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To Neoproterozoic Timan-Varanger Belt Along the Northeastern Margin of Baltica Polarforschung 68: 267 - 274,1998 (erschienen 2000) Teetonics and Sedimentation of the Meso- to Neoproterozoic Timan-Varanger Belt along the Northeastern Margin of Baltica By Vsevolod G. Olovyanishnikov', David Roberts? and Anna Siedleekat THEME 8: Polar Urals, Novaya Zemlya and Taimyr: The North­ "Tirnanides'. Subsequent research by several Russian scientists, ern Connection of the Uralides in particular ZHURAVLEV and co-workers (e.g. ZHURAVLEV & GAFAROV 1959, ZHURA VLEV & OSADCHUK 1960, 1962, Summary: Extending from the Timans in the southeast to the Varanger Penin­ ZHURAVLEV 1972) and RAZNITSYN (e.g., 1962, 1968), brought a sula in the northwest, the Timan-Varanger Belt (TVB) comprises predominantly wealth of data and ideas on several aspects of the geology of the terrigenous Neoproterozoic successions, defonned and metamorphosed at corn­ paratively low grade during the Timanian (Baikalian) orogeny, an event broadly Timans and also on the relationship between this Neoproterozoic equivalent to the Cadomian 01' western Europe, In Neoproterozoic time the TVB fold belt and the pre-Palaeozoic substratum of the Pechora Ba­ formed the faul ted, extensional southwestern margin 01' an oceanic basin, the sin, In addition, several decades of research by GETSEN (sum­ central parts 01' which are buried beneath the Palaeozoic and youngcr cover 01' marised in OLOVYANISHNIKOV 1975, 1987, 1998) have resulted the Pechora Basin. The major structural element 01' the basin margin is a NW­ SE-trending fault zone thar separated two domains 01' sedimentation; pericratonic in further and considerable progress in our knowledge of the to the southwest and basinal to the northeast, which show contrasts in both thick­ geology of the Timanides, ness and sedimentary fucies. In the Timan-Kanin-Pechora part 01' the basin, sedi­ mentation began already in the Middle Riphean, and by Late Riphean time a The northwestern extension ofthe Timanian mountain chain was prominent stromatolitie carbonate ramp formation had built up along the shelf margin. In the NW Kola- Varanger region, however, sedimentation did not start postulated by RAMSAY (1899) and TSCHERNYSCHEV (1901) to oc­ until thc (?)Middle-Late Riphean. Thus, with time, the basin extended cur along the northeastern Murmansk Coast of the Kola Penin­ northwestwards anelsedimentation, including deposition ofVarangerian tillites sula, on Rybachi, Sredni and Kildin, and to continue far into in the northwest, continued into the Vendian period. The fault zone which formed northern Norway. Potential field and seismic ret1ection data in the extensional margin of the basin was reactivated during the Timanian orogeny and again in later periods. The Timanian deformation in these exposed marginal offshore areas has confirmed the presence of these folded rocks areas involved basinal inversion, folding and oleavage development, arising from immediately northeast of Kola (e.g., BOGATSKY et al. 1996), SW-directed compressivc stresses, the main phasc 01' these movements dating Recently, a modified version of this idea, which had been ac­ to about 600-575 Ma, A variety 01' felsic to mafic plutons and dykes intruded cepted for decades in several large-scale geological interpreta­ the folded rocks 01' thc TVB. tions, received new support from some of the results of a joint Both seismic reflection and deep drill hole data have shown that Meso- to Neo­ Norwegian-Russian research programme carried out during the proterozoic strata in the prc-Palaeozoic basement of thc Pechora Basin are more years 1989-95 on the coastal Neoproterozoic occurrences ofthe intcnsivcly deformed and metamorphoscd and also include oceanic and are Kola Peninsula and on Varanger Peninsula in Norway (see in volcanic scqucnccs and diverse plutonic rocks. Fragments 01' older basement terranes arc also present. Timanian deformation beneath the Pechora Basin was ROBERTS & NORDGULEN 1995). The latter area, now inferred to thus much more intcnsc and involved the telcscoping 01' arcs, are roots and expose the northwesternmost segment of the proposed chain, microcontinental terranes in a more complex accretionary zone, generally re­ had already been thoroughly mapped and studied by geologists fcrrcd to as the Pechorskaya eollision zone. of the Geological Survey of Norway and other western work­ ers since the mid-1960s. Finally, all three authors ofthis paper together visited the Central Timans in 1995 (OLOVY ANISHNIKOV INTRODUCTION et al. 1997). The Timanian mountain chain, an important regional element The objective of this contribution is to outline the recent pro­ in Circum-Barentsian geological structure, was first recognised gress and understanding of this about 1800 km-long Neopro­ almost precisely 100 years ago (RAMSA Y 1899, TSCHERNYSCI-IEV terozoic structural element occurring along the northeastern 1901). SCHATSKY (1935, 1958) further developed this early idea perimeter of the Baltic Shield and Russian Platform. In the text and suggested that the chain represented part of a Late which follows we refer to Schatsky's "Timanides: as the Timan­ Precambrian Baikalian fold belt which he called the Varanger Belt (TVB) in which the Timans themselves consti­ tute the geographically most extensive, southeastern part. 1 Institute of Gcology, Komi Research Centre, Ural Division, Russian Academy of Sei­ Note: Neoproterozoic = Late (Upper) Proterozoic = 1000 (900) enees, Pervomaiskaya 54, Syktyvkar, 167000 Russia. Ma - 545 Ma = Late (Upper) Riphean and Vendian. Norges Gcologiske Undersokelse, N-7491 Trendheim. Norway Mesoproterozoic = 1600-1000 Ma = Lower (Early) and Mid­ Manusript received 14 Deeember 1998, accepled 12 Ocrober 1999. dIe Riphean. 267 STRATIGRAPHY AND SEDIMENTATION Sediments and sedimentation realms: general features The Meso- to Neoproterozoic strata of the Timan-Varanger Belt accumulated in response to extensiona1 faulting along the north­ eastern perimeter of the Fennoscandian Shield. The pre­ dominantly terrigenous sedimentary successions also include an extensive be1t of carbonate rocks in the Timan-Kanin zone. The rocks are for the most part metamorphosed at on1y very low grade. On the Kanin Peninsula and in northern Timans, how­ ever, metamorphic grade reaches up to amphibolite facies, par­ ticularly in the cores of anticlines. Two parallel, NW-SE­ trending, elongate, sedimentation domains are present adjacent to the major zone of faulting which played a crucia1 role in the development and character of sedimentation on either side of this structural element (Fig. 1). The fault zone exposed on the Varanger and Rybachi-Sredni Peninsulas, the Trollfjorden­ Komage1va Fault Zone (TKFZ) and Sredni-Rybachi Fault Zone (SRFZ), respectively, can be followed to the southeast along and just off the coast of the Kola Peninsula, partly with the help of geophysical data. It then extends across the Kanin Peninsula and into the Timans where it is known as the Central Timan Fault (CTF). It is fairly weIl documented that the CTF formed the southwestern margin of a Neoproterozoic (Riphean) basin bur­ ied beneath unconformably overlying Cambro-Ordovician rocks of the adjacent Pechora Basin where there are also several other parallel faults. The prolongations of these other faults beneath the Barents Sea are generally poorly known. The CTF-SRFZ­ Z TKFZ, on the other hand, not only continues throughout the <t: CI: Timan-Varanger Belt but also clearly separates the two, above­ w co mentioned, distinct domains of sedimentation: pericratonic to ~+ + cn the southwest and basinal to the northeast, the D-,- lithostratigraphica1 successions of which show contrasts in both ~ 3 7 thickness and sedimentary facies towards the northwest. 4 8 A form of zonation in the Timans, involving lithology, con­ 9 trasting thicknesses and degree of metamorphism, but not sedi­ Fig. 1. Top: Outline map showing the Timan-Varanger Belt. KP - Kanin Penin­ mentation domains, had, in fact, already been suggested some sula; NT - Northern Timan; RP - Rybachi Peninsula; SP - Sredni Peninsula; VP 40 years ago (ZHURAVLEV & OSADCHUK 1960). - Varanger Peninsula; CTF - Central Timan Fault; ETF - East Timan Fault; WTF - West Timan Fault. The CTF is shown to continue to the Rybachi-Sredni and The lithological development of both the pericratonic and the Varanger Peninsulas where it is called Sredni-Rybachi Fault Zone and Trollfjorden-Komagelva Fault Zone, respectively. Shaded areas show the out­ basinal successions ofVaranger, Rybachi, Sredni, Kildin, Kanin, crop of the Neoproterozoic rocks. and northern and centra1 Timans varies considerably along Bottom: Simplified geological-structural map ofthe Timan Range and basement strike, a feature which is not unexpected in view of the great of the Pechora Basin. 1: Basement; 2: Pericratonic zone; 3: Carbonate shelf distances involved, the likely differential stresses operative margin; 4: Slope-to-basin zone; 5: Pechora collision zone 6: Outcrop of the Meso- to Neoproterozoic rocks; 7: Zone ofTimanian accretion, 8: Urals; 9: Line along the basin-margin faults, and a varying topography in the of the section, shown in Figure 4. WTF: West Timan Fault (also called the Pre­ adjacent source areas. These variables, along with the fact that Timan Fault); CTF: Central Timan Fault; ETF: East Timan Fault; NT: North­ the ages of the successions are generally only roughly deter­ ern Timan; PK: Pechora-Kozhva Fault; Kol. M.: L. Precambrian Kolguev mas­ mined by microfossils and indirectly by isotopic ages of sif or terrane; Kho.M.: L. Precambrian Khoreyver massif 01'
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